RESISTIVITY AND CHARGEABILITY SIGNATURES OF TSUNAMI DEPOSITS AT ACEH BESAR AND BANDA ACEH COASTAL AREA,
INDONESIA
Muhammad Syukri 1,2, Rosli Saad 3*, Sabrian Tri Anda2, and Zul Fadhli2
1Department of Physics, Faculty of Sciences, Syiah Kuala University, Banda Aceh, Indonesia
2Department of Engineering Geophysics, Syiah Kuala University, Banda Aceh, Indonesia
3School of Physics, Universiti Sains Malaysia, 11800 Penang, Malaysia
*Corresponding Author, Received: 03 Jan. 2019, Revised: 20 Jan. 2019, Accepted: 08 Feb. 2019 ABSTRACT: The study was conducted at the coastal area of Aceh Besar and Banda Aceh using 2-D resistivity and IP methods to investigate the changes/response of resistivity and chargeability toward sediment. The study is aimed to identify the post-, pre- and tsunami sediment deposits. The results are validated with hand auger performed on the study line. Generally, the study identified that the coastal sediments of Aceh Besar and Banda Aceh consist of clay/silty clay/sand/silty sand. Based on the results, the sediments are categorized into three layers; the top layer (post-tsunami sediment), tsunami sediments and pre-tsunami sediments. The tsunami sediment consists of a mix of sand or clay or silty clay or silty sand. Each layer was represented by different resistivity and chargeability values depending on the sediment types.
Keywords: Resistivity, Chargeability, Hand Auger, Post-, pre-, and tsunami sediment deposits.
1. INTRODUCTION
The great earthquake and tsunami that occurred at Aceh on 26 December 2004, affecting several countries in South East Asia have left many pieces of evidence to be observed. The event triggered researchers to investigate in detail and gain knowledge for future hazards related to earthquakes and tsunamis. It is believed that the tsunami deposit sediments left by the event can be used to improve risk assessment. Studies on the tsunami deposit sediments play an important role in identifying the past earthquake and tsunami event and expand the knowledge of magnitude and frequency of the event [1]. Jaffe and Gelfenbaum [2] stated that the world record of tsunamis studies is limited, thus contributing to the imprecise tsunami risk assessment. Moore et al. [3] ascertain that tsunami deposit sediments have been studied in several locations but only in smaller modern tsunamis event such as the Flores incident in 1992 [4], [5]; 1993 Okushiri [6], [7]; 1994 Java [8]; and 1998 Papua New Guinea [9]. Nevertheless, research about the tsunami deposit sediments caused by large scale tsunamis such as Aceh tsunami is limited since the natural event itself rarely occurs. This paper discusses the tsunami deposit sediments caused by the great earthquake and tsunami events that occurred in Aceh in 2004. The study takes place at two sites along the coastal line of Banda Aceh and Aceh Besar, Indonesia. Identifications of the
tsunami deposit sediments are done by employing geophysics method (2-D resistivity and induced polarization) and validated with hand auger data.
2. GEOLOGY OF STUDY AREA
Generally, the lithology of Aceh Besar district is made up of alluvium composed of gravel, sand, sandy clay, sandy silt, clayey silt, silty clay and sediments originated from the swamp. The topography of the area is considered as undulating, spread out from northwest to southeast. The district is also known as Krueng Aceh basin [10], [11]. The rock types are classified as Tertiary and Pre-tertiary rock while the eastern part delimited with hills composed of Plio-Plistosen which originated from Seulawah Agam Volcano [12]. Generally, Banda Aceh district is situated at the deltaic plains of Krueng Aceh which is specifically located between the low Tertiary and Quaternary volcanic hills on eastward and Cretaceous limestone hills in the west.
According to Culshaw et al. [13], the soil of the area was made up by alluvium and marine sediments with an approximate thickness of 179 m which is deposited from the graven structure in the Sumatran Fault System. The rocks of this area are classified as limestone, slates and phyllites at the western part while the east side is composed of deposited andesitic tuffs and subsidiary flows (Figure 1).
Fig. 1: General geology of Aceh
The tsunami deposit sediments study was conducted at two locations (Kajhu 1 and Kajhu 2) in Aceh Besar district and two locations (Tibang 1 and
Tibang 2) in Banda Aceh district using electrical method (2-D resistivity and induced polarization) together with hand auger (Figure 2).
Fig. 2: Study locations of tsunami deposit sediments; two in Aceh Besar district and two in Banda Aceh district (Google Earth, 2018).
3. METHODOLOGY
The electrical method applied in the study areas is 2-D resistivity and induced polarization (IP) using the ABEM SAS4000 Terrameter system. Two sets of Lund cables with 21 take-outs each and 41 electrodes were employed by applying pole-dipole
array considering this type of array has the deepest depth penetration and provides a good horizontal and vertical resolution. Table 1 shows the acquisition settings of ABEM SAS4000 in measuring the resistivity and IP values for all the survey lines. The data acquisition applied multiple period windows of time of 20 ms and the cut-off
frequency of 50 Hz used to suppress power line noise.
Table 1: ABEM SAS4000 settings for data acquisition of resistivity and IP.
Item Setting
Current on 1.0 second Current off 1.0 second Acquisition delay 0.4 second Acquisition time 0.6 second Measuring window 10
The first study area is at Kajhu sub-district of Aceh Besar district. Two survey lines were set at two locations and each location consists of one survey line, Kajhu 1 and Kajhu 2 respectively (Figure 3a and 3b). Kajhu 1 survey line was conducted using 2-D resistivity and induced
polarization using minimum electrode spacing of 0.2 m and pole-dipole array. The hand auger (HA1) for the Kajhu 1 was located at 4 m along the survey line. Kajhu 2 survey line was conducted using 2-D resistivity and induced polarization using minimum electrode spacing of 0.5 m and pole-dipole array, but the hand auger for the Kajhu 2 was not performed due to site restriction. The second study area is at Tibang sub-district of Banda Aceh district.
Two study locations are set, each location consists of one survey line, Tibang 1 (Figure 3c) and Tibang 2 (Figure 3d). The survey lines (Tibang 1 & 2) were conducted using 2-D resistivity and induced polarization using minimum electrode spacing of 0.2 m with the pole-dipole array. Hand augers (HA2 and HA3) were performed at 4 m along each survey line respectively. Table 2 shows the coordinate of the survey lines and hand augers.
Fig. 3: Survey lines at Aceh Besar; (a) Kajhu 1, (b) Kajhu 2, and Banda Aceh; (c)Tibang 1 and (d) Tibang 2 (Google Earth, 2018)
Table 2: The coordinates of the survey lines and hand augers.
Name Distance (m) Latitude (o) Longitude (o)
Kajhu 1 0 5.606306 95.373361
8 5.606250 95.373306
Kajhu 2 0 5.597918 95.372060
20 5.597767 95.372169
Tibang 1 0 5.588222 95.342306
8 5.588154 95.342336
Tibang 2 0 5.593203 95.335600
8 5.593131 95.335611
HA1 4 5.606280 95.373336
HA2 4 5.588189 95.342322
HA3 4 5.593171 95.335607
4. RESULTS AND DISCUSSION
Figure 4 depicts the range of resistivity values obtained. Generally, the resistivity values of the study sites are in the 0 to 15 Ohm. m range and the
chargeability values are between -15 to 850 ms (Figure 4).
Fig. 4: 2-D resistivity and IP results for the study areas; (a-b) Kajhu 1, (c-d) Kajhu 2, (e-f) Tibang 1, and (g-h) Tibang 2.
Figure 5 shows the hand auger results. The results indicate HA1 and HA2 are dominated by clay/silty clay while HA3 is dominated by sand/silty sand. Generally, the hand auger results show three types of sediments deposit. Post-tsunami sediments
are located at the top of the ground surface with a depth of 0.11-0.8 m, followed by tsunami sediments deposit with the depth of 0.29-1.58 m while pre- tsunami sediment deposit was identified beyond the tsunami sediments deposit.
0 1 2 3 4 5 6 7 8 9 10 11 12 13 14 15 16 17 18 19 20
Distance (m)
-8 -7 -6 -5 -4 -3 -2 -1 0
Depth (m)
0 1 2 3 4 5 6 7 8
Distance (m)
-3 -2 -1 0
Depth (m)
0 1 2 3 4 5 6 7 8
Distance (m)
-3 -2 -1 0
Depth (m) 0 0.18 0.24 0.31 0.4 0.53 0.69 0.9 1.18 1.54 2 2.62 3.42 4.47 5.83 7.62 9.95 14.95
0 1 2 3 4 5 6 7 8 9 10 11 12 13 14 15 16 17 18 19 20
Distance (m)
-7 -6 -5 -4 -3 -2 -1 0
Depth (m)
0 1 2 3 4 5 6 7 8
Distance (m)
-3 -2 -1 0
Depth (m)
0 1 2 3 4 5 6 7 8
Distance (m)
-3 -2 -1 0
Depth (m)
0 1 2 3 4 5 6 7 8
Distance (m)
-3 -2 -1 0
Depth (m)
0 1 2 3 4 5 6 7 8
Distance (m)
-3 -2 -1 0
Depth (m)
Ohm.m -15 -5 -2 -0.5 0 0.5 5 10 30 50 100 150 200 250 300 400 500 810.1 msec (A)
(C)
(E)
(G)
(B)
(D)
(F)
(H)
Fig. 5: Hand auger results of the study area; (a) HA1, (b) HA2 and (c) HA3
Figure 6 and 7 show the 2-D resistivity sections of Kajhu 1 and Tibang 1, correlated with hand auger results (HA1 and HA2 respectively). The results indicate the post-tsunami sediment resistivity value is <0.53 Ohm.m, tsunami sediment is 0.53-0.9 Ohm.m and pre-tsunami sediment is >0.9 Ohm.m.
The hand auger samples show that the sediments are dominated by clay/silty clay. Tibang 2 (Figure 8) results indicate the post-tsunami sediment
resistivity value is <2 Ohm.m, tsunami sediment is 2-3.42 Ohm.m and pre-tsunami sediment is >3.42 Ohm.m, and the hand auger samples show that the sediments are dominated by sand/silty sand.
Referring to the resistivity values of Kajhu 1, Tibang 1 and 2, the Kajhu 2 section (Figure 9) is interpreted as tsunami sediment (2-3.42 Ohm.m) and pre-tsunami sediment (>3.42 Ohm.m), and the sediments are dominated by sand/silty sand.
Fig. 6: Correlation between resistivity section of Kajhu1 and hand auger for sediment identification
Fig. 7: Correlation between resistivity section of Tibang 1 and hand auger for sediment identification
Fig. 8: Correlation between resistivity section of Tibang 2 and hand auger for sediment identification
Fig. 9: Correlation between resistivity section of Kajhu2 and hand auger for sediment identification Figures 10 and 11 show the 2-D chargeability
sections of Khaju 1 and Tibang 1, correlated with hand auger respectively. The results indicate the post-tsunami sediments chargeability value is 150- 300 ms, tsunami sediment is 0.5-500 ms and pre- tsunami sediment is >100 ms. The hand auger samples show that the sediments are dominated by clay/silty clay. Tibang 2 (Figure 12) results indicate that the post-tsunami sediment chargeability value
is 50-100 ms, tsunami sediment is 10-50 ms and pre-tsunami sediment is >10 ms, and the hand auger samples show the sediments are dominated by sand/silty sand. Referring to the chargeability values of Khaju 1, Tibang 1 and 2, the Khaju 2 section (Figure 13) is interpreted as tsunami sediments (0.5-500 ms) and pre-tsunami sediments (>100 ms), and the sediments are dominated by sand/silty sand.
1 2 3 4 5 6 7
Distance (m)
-3 -2 -1 0
Depth (m)
0 0.18 0.24 0.31 0.4 0.53 0.69 0.9 1.18 1.54 2 2.62 3.42 4.47 5.83 7.62 9.95 45.454 Ohm.m
0 m 0.11 m 0.29 m
Auger depth (m) Post-tsunami
sediment
Tsunami sediments
Pre-tsunami sediments
Fig. 10: Correlation between IP section of Kajhu1 and hand auger for sediment identification
Fig. 11: Correlation between IP section of Tibang 1 and hand auger for sediment identification
Fig. 12: Correlation between IP section of Tibang 2 and hand auger for sediment identification
Fig. 13: Correlation between IP section of Kajhu 2 and hand auger for sediment identification
5. CONCLUSIONS
Tsunami sediment consists of a mix of sand or clay or silty clay or silty sand. The mixture depends on the size of the water waves and ground topography.
Post-tsunami sediments refer to sediments that occur after the tsunami event which comes from erosion or seawater wave activities, meanwhile pre-
tsunami sediments refer to sediments that occur before tsunami event which also comes from erosion or seawater wave activities. Table 3 shows the distribution of resistivity and chargeability values for post-tsunami, tsunami and pre-tsunami sediments related to sediments types.
Table 3: Resistivity and chargeability values of the post-tsunami, tsunami and pre-tsunami sediments at Aceh Besar, Indonesia.
Event Sediment type Resistivity (Ohm.m) Chargeability (ms.) Post-tsunami clay/silty clay <0.53 150-300
sand/silty sand <2 50-100
Tsunami clay/silty clay 0.53-0.9 0.5-500
sand/silty sand 2-3.42 10-50
Pre-tsunami clay/silty clay >0.9 >100 sand/silty sand >3.42 >10
6. ACKNOWLEDGMENTS
The authors would like to thank the Ministry of Research, Technology and Higher Education, Indonesia for financial support in the scheme of PCP-PNBP Unsyiah 2018 Grant. Special thanks are extended to technical staffs of geophysics
laboratory and geophysics postgraduate students, Universiti Sains Malaysia and geophysics students, Faculty of Sciences and Faculty of Engineering, Syiah Kuala University (Aceh).
7. REFERENCES
[1] Dawson, A. G., Foster. I. D. L., Shi. S., Smith.
D. E. and Long. D., The Identification of Tsunami Deposits In Coastal Sediment Sequences, Science of Tsunami Hazards, Vol.
9, 1991, pp. 73-82.
[2] Jaffe, B. E., & Gelfenbaum, G., Using tsunami deposits to improve the assessment of tsunami risk, in Proc. Proceedings of the Solutions to Coastal Disasters 2002 Conference, 2002, pp. 836-847
[3] Moore, A., Nishimura, Y., Gelfenbaum, G., Kamataki, T., & Triyono, R., Sedimentary Deposits Of The 26 December 2004 Tsunami on The Northwest Coast of Aceh, Indonesia, Earth, Planets and Space, Vol. 58, Issue 2, 2006, pp. 253-258.
[4] Minoura, K., Imamura, F., Takahashi, T.,
&Shuto, N, Sequence of Sedimentation Processes Caused by The 1992 Flores Tsunami: Evidence From Babi Island, Geology, Vol. 25, Issue 6, 1997, pp. 523-526 [5] Shi, S., Dawson, A. G., & Smith, D. E.,
Coastal Sedimentation Associated with The December 12th, 1992 Tsunami in Flores, Indonesia, Pure and Applied Geophysics, Vol. 144, Issue 3-4, 1995, pp. 525-536.
[6] Nishimura, Y., & Miyaji, N., Tsunami Deposits From The 1993 Southwest Hokkaido Earthquake and The 1640 Hokkaido Komagatake Eruption, Northern Japan, Pure and Applied Geophysics, Vol.
144, Issue 3-4, 1995, pp. 719-733.
[7] Sato, H., Shimamoto, T., Tsutsumi, A., &
Kawamoto, E., Onshore Tsunami Deposits Caused by The 1993 Southwest Hokkaido And 1983 Japan Sea Earthquakes, Pure and Applied Geophysics, Vol. 144, Issue 3-4, 1995, pp. 693-717.
[8] Dawson, A. G., Shi, S., Dawson, S., Takahashi, T., & Shuto, N., Coastal Sedimentation Associated with The June 2nd and 3rd, 1994 Tsunami In Rajegwesi, Java, Quaternary Science Reviews, Vol. 15, Issue, 8-9, 1996, pp. 901-912.
[9] Gelfenbaum, G., & Jaffe, B., Erosion and Sedimentation From The 17 July 1998 Papua New Guinea Tsunami, Pure and Applied Geophysics, Vol. 144, Issue 3-4, 1995, pp.
525-536.
[10] IWACO, Kabupaten Aceh Barat: Planning for Water Supply Development and Raw Water Sources Allocation. In: Study of Water Sources Allocation for Water Supply for D.I.
Aceh Province, prepared in association with COWI Consulting Engineers and Planners AS, PT. YODYA KARYA Architects &
Consulting Engineers & PT. GAMMA EPSILON Consulting Engineers for Government of Indonesia, Ministry of Public Works, Directorate General of Human Settlements, Directorate of Water Supply, Banda Aceh, 1993.
[11] Farr, J.L. and Djaeni, A., A Reconnaissance Hydrogeological Study of the Krueng Aceh Basin, North Sumatra, Bandung, 1975.
[12] Moechtar, H., Subiyanto, S., & Sugianto, D., Alluvial Geology and Characteristics of Coastal/Beachfront deposits in The Valley of
Krueng Aceh, Aceh Besar (prov. Nad), Geologi Aluvium dan Karakter Endapan Pantai/Pematang Pantai di Lembah Krueng Aceh, Aceh Besar (Prov. Nad), Jurnal Geologi dan Sumber Daya Mineral, Vol. 19, Issue 4, 2009, pp. 273-283.
[13] Culshaw, M. G., S. V. Duncan, and N. R.
Sutarto, Engineering Geological Mapping of
The Banda Aceh Alluvial Basin, Northern Sumatra, Indonesia, Bulletin of the International Association of Engineering Geology, Vol. 19, Issue 1, 1979, pp. 40-47.
[14] Google Earth, 2018
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INTERNATIONAL JOURNAL OF GEOMATE
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International Journal of GEOMATE
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ISSN 21862990, 21862982 Coverage 2011-ongoing
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Building and Construction 2012 Q4
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2012 2013 2014 2015 2016 2017 2018
Building and Construction Environmental Engineering Geotechnical Engineering and Engineering Geology Soil Science
2012 2013 2014 2015 2016 2017 2018 0.1
0.2 0.3 0.4
Cites / Doc. (4 years) 2011 0.000 Cites / Doc. (4 years) 2012 0.158 Cites / Doc. (4 years) 2013 0.194 Cites / Doc. (4 years) 2014 0.400 Cites / Doc. (4 years) 2015 0.415 Cites / Doc. (4 years) 2016 0.748 Cites / Doc. (4 years) 2017 0.736 Cites / Doc. (4 years) 2018 0.697 Cites / Doc. (3 years) 2011 0.000 Cites / Doc. (3 years) 2012 0.158 Evolution of the total number of citations and journal's
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S lf Cit 2011 0
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Year International Collaboration 2011 10.53
2012 13 95 Citable documents Non-citable documents
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Documents Year Value
Uncited documents 2011 0 Uncited documents 2012 17
0.4 0.6
2011 2012 2013 2014 2015 2016 2017 2018 0
250 500
2011 2012 2013 2014 2015 2016 2017 2018 0
0.4 0.8
2011 2012 2013 2014 2015 2016 2017 2018 6
12 18 24
0 300 600
0 300 600
Mohammed Ali Al-Bared 1 year ago Thanks a lot for your response
But the thing that i am still wondering is that for year 2016, the category of Building and construction was rated as Q2. Why it changed suddenly? although year 2016 has passed
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Thanks again reply
Mohammed Al-Bared 1 year ago Dear Sir / Madam,
I published my paper in the International Journal of GEOMATE few months ago and my paper was categorized under Building and construction materials. For year 2017, this category (Building and Construction) was under Quartile 2 in SJR. The rules of my university is to publish in at least Q2 Journals and that is why i selected this journal for my publication. Surprisingly, the Q of the
Building and Construction category changed to Q3 although the year 2017 has passed. I really don't understand this sudden change. Can you please clarify this?
Thanks a lot reply
M
Elena Corera 1 year ago Dear Mohammed Al-Bared,
thank you very much for your particiation. According to your question, each year Scopus
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